Pb Isotope Geochemistry of the Late Miocene–Pliocene Volcanic Rocks

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Pb Isotope Geochemistry of the Late Miocene–Pliocene Volcanic Rocks J. Earth Syst. Sci. (2019) 128:167 c Indian Academy of Sciences https://doi.org/10.1007/s12040-019-1185-7 Pb isotope geochemistry of the late Miocene–Pliocene volcanic rocks from Todeshk, the central part of the Urumieh–Dokhtar magmatic arc, Iran: Evidence of an enriched mantle source Mahnaz Khodami Department of Geology, Yazd University, Yazd, Iran. e-mail: Khodami [email protected] MS received 12 July 2018; revised 8 February 2019; accepted 19 March 2019; published online 17 June 2019 The late Miocene–Pliocene volcanic rocks from Todeshk, south-east of Isfahan, are located in the middle of the Urumieh–Dokhtar magmatic belt. The belt is considered the subduction-related magmatic arc. The late Miocene–Pliocene calc-alkaline volcanic rocks are mainly andesite and dacite. The rocks have been formed during the post-collisional stage of the Zagros orogen. Geochemical data show the enrichment of light rare-earth elements and large ion lithophile elements such as Cs, Rb, K, Pb, Ba and Th as well as the depletion of elements with high field strength such as Nb, Ta and Ti. The Pb–Sr–Nd isotopic ratios of the studied rocks are characterised by 206Pb/204Pb = 18.41–18.72; 207Pb/204Pb = 15.64– 15.67; 208Pb/204Pb = 38.49–38.83; 207Pb/206Pb = 0.8372–0.8496; 208Pb/206Pb = 2.0743–2.0905; 87Sr/86Sr = 0.7051–0.7068 and 143Nd/144Nd = 0.5125. The rocks have Δ7/4Pb = 15.44–15.82 and Δ8/4Pb = 57.26–60.44. Based on petrological studies and the whole rock Pb, Sr and Nd isotopes data, the late Miocene–Pliocene calc-alkaline volcanic rocks have been generated from the partial melting of the subduction-related metasomatised mantle. Additionally, the slab-derived melts and fluids were recycled into the mantle source. The data demonstrate that terrigenous sediments accompanied by a subducted slab play an important role in the formation of the enriched mantle as the source of volcanic rocks. Keywords. Pb isotopes geochemistry; calc-alkaline; enriched mantle; Urumieh–Dokhtar magmatic arc; Zagros orogen; Iran. 1. Introduction opening and closure of the Neo-Tethys Ocean (Alavi 1980, 2004; Omrani et al. 2008; Davoudian The late Miocene–Pliocene volcanic rocks in et al. 2016). The Zagros orogen is a part of the Todeshk are significant constituents in the stud- Alpine–Himalayan orogenic belt and consists of ied area. The volcanic rocks are situated in the parallel tectonic subdivisions from the south-west middle of the Urumieh–Dokhtar magmatic arc to the north-east: (i) The Zagros simply folded (UDMA), about 120 km south-east of Isfahan belt and the main Zagros thrust, which is sug- (figure 1a). The UDMA is a large magmatic belt gested to be the suture zone between Gondwana in the Zagros orogen, which is the result of the and Eurasia; (ii) the Sanandaj–Sirjan zone which 1 0123456789().,--: vol V 167 Page 2 of 11 J. Earth Syst. Sci. (2019) 128:167 Figure 1. (a) Position of the studied area in the structural units of Iran (Mohajjel et al. 2003) and (b) the geological map of the studied area (simplified from the geological map of 1:250,000 Nain, Nabavi and Amidi 1978). Figure 2. Representative photomicrographs for dacites (a) consisting of plagioclase phenocrysts and microphenocrysts of amphibole, biotite, quartz and (b) quartz and plagioclase in felsitic groundmass (CPL, field of view 4 mm), representative photomicrographs of andesites, (c) comprising plagioclase, pyroxene and amphibole with a glomeroporphyritic texture and (d) comprising plagioclase and pyroxene with a porphyritic texture (CPL, field of view 4 mm). Bi = biotite, Amp = amphibole, Px = pyroxene, Pl = plagioclase, and Qz = quartz. J. Earth Syst. Sci. (2019) 128:167 Page 3 of 11 167 Table 1. Whole-rock isotopic data of volcanic rocks. AR2 DH7 OG4 RS2 TO4 Sample Andesite Dacite Dacite Dacite Andesite 207 206 Pb/ Pb 0.849556 0.844521 0.84897 0.837225 0.846509 2σ 0.00001 0.00001 0.00001 0.00001 0.00001 208 206 Pb/ Pb 2.090523 2.084596 2.089768 2.074348 2.0850746 2σ 0.00003 0.00004 0.00003 0.00003 0.00003 207 204 Pb/ Pb 15.64101 15.65614 15.64264 15.67378 15.65264 2σ 0.00087 0.00077 0.00077 0.00079 0.00063 208 204 Pb/ Pb 38.48755 38.64418 38.50355 38.83326 38.56566 2σ 0.00222 0.00204 0.00190 0.00202 0.00142 206 204 Pb/ Pb 18.410571 18.53825 18.42523 18.72091 18.49061 2σ 0.00096 0.00075 0.00081 0.00081 0.00061 87 86 Sr/ Sr 0.705096 0.705925 0.706396 0.706096 0.706792 2σ 0.000031 0.000022 0.000021 0.000017 0.000082 143 144 Nd/ Nd nd 0.512525 nd 0.512552 nd 2σ 0.00002 0.00001 Δ7/4Pb* 15.5210 15.6591 15.5331 15.4432 15.8255 Δ8/4Pb** 60.2178 60.444 60.0344 57.2675 58.3519 207 204 206 204 *Δ7/4Pb = 100 9 [( Pb/ Pb) − 0.1084 9 ( Pb/ Pb) − 13.491] (Hart 1984). nd: not detected. 208 204 206 204 ** Δ8/4Pb = 100 9 [( Pb/ Pb) − 1.209 9 ( Pb/ Pb) − 15.627]. is the internal part of the Zagros orogen consisting of metamorphic complexes and igneous plutons (St¨ocklin 1968; Davoudian et al. 2016) and (iii) the UDMA, which is a subduction-related mag- matic arc along the active margin of the Iranian plate (Berberian and Berberian 1981; Alavi 1994, 2004; Omrani et al. 2008). Magmatic activity in the UDMA created a wide belt of mostly Ceno- zoic volcanic and plutonic rocks. The UDMA is located between the Sanandaj–Sirjan zone and the Central Iran structural zone (figure 1a) (Berbe- rian and Berberian 1981; Mohajjel et al. 2003). The maximum magmatic activity in the UMDA occurred in the Eocene period, but after a period of inactivity, has continued during the upper Miocene to the Plio-Quaternary (Omrani et al. 2008). However, the studies indicate that a colli- sion occurred in the Oligocene–late Miocene, and Figure 3. Classification of the volcanic rocks in the TAS dia- although the active subduction between the Ira- gram (Cox et al. 1979; data from Khodami et al. 2010). nian edge of Eurasia and the Arabian plate as a part of Gondwana had ended, the magmatic activ- sediments or releasing of fluids by the dehydration ity did not stop (Berberian and Berberian 1981; of the subducting oceanic slab (Tatsumi and Taka- Hassanzadeh 1993; Ghasemi and Talbot 2005; hashi 2006). Pb isotope data can demonstrate the Omrani et al. 2008). The late Miocene to the Plio- origin and proportion of involvement of mantle, Quaternary volcanism in the UDMA belongs to the slab, sediments or continental crust in the gener- post-collision magmatic activity which is probably ation of parental magma. 204Pb is non-radiogenic, the result of a break off the Neo-Tethys slab while 208Pb/204Pb, 207Pb/204Pb and 206Pb/204Pb (Omrani et al. 2008). Magmatism in a subduction- increase during U and Th decays (Faure 1986). related setting originates from the partial melting The most important mantle sources are identified of the mantle wedge, lower crust, oceanic slab, slab by isotopic features as depleted mid-ocean ridge 167 Page 4 of 11 J. Earth Syst. Sci. (2019) 128:167 Figure 4. (a) Chondrite-normalised REE element patterns of volcanic rocks (chondrite-normalising values are from Nakamura (1974). (b) Primitive mantle-normalised patterns of volcanic rocks. Normalising values are from Sun and Mcdonough (1989) (data from Khodami et al. 2010). Figure 5. (a) La/Yb vs. Yb diagram, (b)Th/Lavs. Ce/Pb diagram, (c) Th/Yb vs. Ba/La diagram and (d) Ba/Th vs. La/Sm diagram of volcanic rocks (Wang et al. 2006; Arslan et al. 2013; Qian et al. 2016; data from Khodami et al. 2010). basalts (MORBs) or the depleted MORB mantle type II (EMII) (Faure 1986; Zindler and Hart (DMM), high mu, mu = 238U/204Pb (HIMU), 1986). The HIMU sources were generated when enriched mantle type I (EMI) and enriched mantle the subducted oceanic crust was dehydrated and J. Earth Syst. Sci. (2019) 128:167 Page 5 of 11 167 remained in the deep mantle for a long period. The the Eocene, including varieties of the volcanic and HIMU have high U/Pb, Th/Pb and Sr/Rb ratios the volcano-sedimentary rocks. Miocene reddish- and indicate the radiogenic evolution of 206Pb grey conglomerate and sandstone as Red forma- and 207Pb (Wilson 1989). The DMM reservoirs tion are the other lithological units (Nabavi and have a U-depleted composition. The EMI has a Amidi 1978). The andesitic lava flows across the geochemical composition similar to the lower crust Upper Red formation. The dacitic domes and or marine pelagic sediments as reported from car- lava domes intruded into the andesite and prob- bonatite metasomatism in the lithospheric mantle ably they belong to the latest volcanic activ- (White 2003; Lustrino and Anderson 2015). The ity in the area (figure 1b) (Nabavi and Amidi EMI sources have high Th/U and low U, Th/Pb 1978). Based on stratigraphy, the volcanic rocks ratios, negative anomalies of Hf, Zr and positive were emplaced during the late Miocene–Pliocene anomalies of Eu. EMI can be formed by recycling after the collision between the Iranian and Ara- the lower continental crust or subducted pelagic bian platforms. One available K–Ar age dating sediments (White 2003; Lustrino and Anderson for a dacitic dome has exhibited 14.1 ± 0.8Ma 2015; Yamgouot et al. 2016). The EMII mantle (Ghorbani et al.
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